AbstractIn their paper on the Montagna dei Fiori area, Storti et alii (2017) present a new geological map and discuss the dolomitization pattern and the Jurassic extensional architecture of this sector of the Central Apennines. They conclude that their "field evidence does not support the gravity-driven olistolith hypothesis proposed by Di Francesco et alii (2010)", which had already been considered "definitively to discard" by Storti et alii (2016). As proponents of such "olistolith hypothesis", we argue in this Discussion that the paper by Storti et alii (2017) does not provide any compelling evidence for a rejection of our original hypothesis.

Besides a simplified geological map of the Salinello Valley, Di Francesco et alii (2010) also presented a sketch map of a larger area, in order to include the four major outcrops of Calcare Massiccio Fm. that constituted the stratigraphic focus of their work, and which were interpreted as exotic blocks. In that map, and following Mattei (1987), the Monte Foltrone area was misrepresented as being mostly occupied by the Corniola Fm., which Storti et alii (2017) partly amended. That particular area was not discussed in Di Francesco et alii (2010), nor will be here. We acknowledge this improvement over the pre-existing literature, and we stand corrected, although our unpublished map of the Monte Foltrone area is still different. It will become apparent to the reader, however, that this has little bearing on this Discussion.

AbstractResedimented calcarenites and hybrid arenites are commonly found interbedded with various Upper Miocene terrigenous units (hemipelagic marls, "brecce della Renga fm.", and siliciclastic turbidites) across the Simbruini Mts. and neighbouring areas of Central Apennines. Their distribution provides evidence for a complex, and rapidly evolving, paleogeography across a region that was experiencing the transition from foreland to accretionary wedge conditions during the Tortonian and Messinian. The bio-sedimentological features of the calcarenites indicate deposition through gravity flows (turbidity currents) sourced by areas of active benthic, heterozoan-type carbonate
production, locally lying at photic depth. Thin-section analysis of >130 samples revealed that the resedimented levels are mainly composed by bioclastic calcarenites, with fragments of bivalves, echinoids, bryozoans, balanids, benthic foraminifera, anellids and red algae, along with subordinate planktonic foraminifera. The calcareous turbidites in the hemipelagic marls (Unità argillosomarnosa) are characterized by the presence of Heterostegina sp., and their main source area was probably lying east, on the undeformed foreland. In contrast, evidence from field mapping, their common association with Cretaceous and Miocene carbonate lithoclasts, and the age of the encasing units, all suggest that the calcarenites in the "brecce della Renga fm." and in the siliciclastic turbidites ("complesso torbiditico altomiocenico laziale-abruzzese") could most likely have a different source.
The presence of a carbonate ridge, corresponding today to the NW sector of the Simbruini range, bordered by normal faults exposing the Cretaceous substrate, is proven proven by mappable paleo - escarpment tracts onlapped by clastic and hemipelagic deposits.
This ridge could have fed surrounding deeper areas with a mixture of lithoclasts and loose bioclastic material, produced through erosion of exposed bedrock coupled with export of sediment that was being produced topping and fringing the footwall blocks and their marginal downsteps. Carbonate production was apparently able to survive for a limited time in small productive areas until the early Messinian, shedding sediment into the siliciclastic foredeep